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SMITHSONIAN MISCELLANEOUS COLLECTIONS 



VOLUME 60. NUMBER 13 



A STUDY OF THE SALINITY OF THE SURFACE WATER 

IN THE NORTH PACIFIC OCEAN AND IN THE 

ADJACENT ENCLOSED SEAS 



BY 
AUSTIN HOBART CLARK 




(Publication 2153) 



CITY OF WASHINGTON 
PUBLISHED BY THE SMITHSONIAN INSTITUTION 
DECEMBER 4, 1912 



Moi^«! 



p^ 



^' -^' I Oh 



SMITHSONIAN MISCELLANEOUS COLLECTIONS 



VOLUME 60, NUMBER 13 



A STUDY OF THE SALINITY OF THE SURFACE WATER 

IN THE NORTH PACIFIC OCEAN AND IN THE 

ADJACENT ENCLOSED SEAS 



BY 
AUSTIN HOBART CLARK 



^ 




(Publication 2153) 



CITY OF WASHINGTON 
PUBLISHED BY THE SMITHSONIAN INSTITUTION 
DECEMBER 4, 1912 



BALTIMORE, MD., U. S. A. 



0. Of Or 

DEC 9 1912 



(^'^4 



\> 



A STUDY OF THE SALINITY OF THE SURFACE WATER 

IN THE NORTH PACIFIC OCEAN AND IN 

THE ADJACENT ENCLOSED SEAS 

By AUSTIN HOBART CLARK 
CONTENTS 

PAGE 

Preface ' ^ 

The limits of error in the observations 4 

The rejection of inaccurate readings 5 

Calculation of the constant representing the instrumental error 6 

Brief resume of the conditions found in the North Pacific 9 

Meteorological conditions tending to lower the salinity of the Pacific, while 

increasing the salinity of the Atlantic I5 

The seasonal variation in the salinity of the water off the Californian 

Coast 15 

The Bering Sea I7 

Synopsis of the salinity observations taken during the 1906 cruise of the 

" Albatross " I9 

Narrative • • ^i 

An observation on the intermingling of river and ocean water 24 

Comparison of figures with those previously published 24 

PREFACE 

During the 1906 cruise of the United States Fisheries steamer 
" Albatross " in the North Pacific Ocean and in the Bering, Okhotsk, 
Japan, and Eastern Seas, I devoted considerable attention to 
the question of the salinity of the water through which the ship 
passed. Though much has been accomplished, thanks chiefly to the 
activity of the Russian Admiralty, in the working out of the con- 
ditions along the Asiatic shores and, thanks to the ships of the 
German merchant marine, both steam and sail, in the elucidation of 
the conditions from Seattle southward, very little has been done on 
the American side north of Puget Sound and in the Bering Sea; 
therefore particular pains were taken to make the records for this 
area especially complete. 

Water specimens were taken by the quartermaster at 8 a. m. and 
at 8 p. m., and at once put into 18 oz. crown glass bottles which 

Smithsonian Miscellaneous Collections, Vol. 60, No. 13 

I 



2 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 6o 

were tightly corked. As a rule samples of the surface water were 
also taken whenever the ship was stopped for dredging. 

On account of the motion of the ship and because of the great 
amount of other more pressing work to be done it was not possible to 
work out the density of the water specimens at sea. They were there- 
fore allowed to accumulate in the laboratory until a harbor or quiet 
anchorage was reached when the accumulation was disposed of. 

The variation in the reading of my salinometers resulting from 
changes in temperature was not known. But any error arising from 
such variation was eliminated so far as possible by taking the read- 
ings always in approximately the same temperature, the water 
samples being stored in a room in which the temperature was at all 
times fairly constant. 

There are three important sources of error involved in the method of 
storing water samples in cork stoppered soft glass bottles until such 
time as determination is possible. The water will dissolve a certain 
amount of the glass, thus mcreasing the density ; irregularities from 
this source, however, are probably negligible so far as my results are 
concerned, because of the large probable error involved in the method 
used. Again the date and time of day, or the station number, were 
written on paper labels and placed in the water ; of course the sizing 
and certain other of the constituents of the paper and of the pencil lead 
dissolved out, increasing the salt content of the water ; but the labels 
used were of uniform size and composition, and the amount of writ- 
ing was always the same so that approximately the same error is 
involved in each reading and may be considered as compensated in 
the general correction applied. The third source of error lies in the 
evaporation through and around the corks ; occasionally there is 
an evident discrepancy due to this cause (as for instance in Nos. 9 
and 12), but ordinarily the error was probably so small as to be, in 
view of the probable error as calculated, negligible. In the rough 
northern waters it was often necessary to retain water samples for 
several days ; but here it was cold and damp and evaporation was 
reduced to a minimum ; in the south determinations could be made 
much more frequently, and this source of error was largely 
eliminated. 

The apparatus used in determining the specific gravity of the 
water was Hilgard's ocean salinometer, and the specific gravities 
were all reduced to the standard temperature of 60° Fahr. ( I5°.56 C.) . 
The tables employed in this reduction are given in the Report of 
the Commissioner of Fish and Fisheries for 1883 (1885), p. 78. 



recalculated to S -/~:ro from the original figures. 



NO. 13 SALINITY OF PACIFIC SURFACE WATER — CLARK 3 

The standard used by Makaroff in his work was S J^^^o , he having 

been induced to recalculate his observations to this standard because of 
its very general use among oceanographers of other nations, especially 
by the Germans. In his monograph he includes the salinity records 
for the Pacific determined by the " Challenger " and other ships 

17:5^ 
1 7. 5' 
The standard used by the Bureau of Fisheries has generally been 

S ^'c^o , though on one or two of the earlier cruises it appears to 

have been S^^b — , corresponding to that of the " Challenger." 

In the following calculation of an empirical correction for my 

IS. ""6° 
figures no account is taken of the difference between S '^^o - and 

17.=;° 
S Tyto for the reason that such slight differences as exist (Professor 

Kriimmel gives an average of —0.00013 for the difference between 

S '''^•■^^ and S ^^'"^o I ^^^ pracitically constant between the extremes 

15-50 17-5 / 

recorded on this cruise. 

In this paper I have employed figures representing the specific 
gravity of the water rather than the amount of dissolved salts ex- 
pressed in grammes per liter for the reason that almost all of the 
previous records for the area under consideration are so given, and 
therefore the use of the older method renders my figures more readily 
comparable with those of previous observers. 

Absolute accuracy is not claimed for the figures representing the 
specific gravities herein recorded ; indeed the author is well aware 
that absolute accuracy cannot possibly be secured by the method 
used under the limitations imposed by a voyage of this character. 
Nansen has shown the difficulties in the way of salinity determination 
by salinometer, even with the precautions taken by him, and in the 
case of my determinations and subsequent calculations the taking of 
any but the most obvious precautions meant the expenditure of a con- 
siderable amount of time and thus became impossible. But the 
figures have a distinct comparative value and, in the absence of 
other data for much of the region covered, may be taken as affording 
an approximate index of the conditions in the seas traversed by the 
ship. 



SMITHSONIAN MISCELLANEOUS COLLECTIONS 



VOL. 60 



As my time was too fully occupied in other work to permit of 
my devoting my personal attention to it, the greater part of the 
actual determination of the densities was done by Mr. Leonard M. 
Tongue, the clerk of the ship, under my supervision. Mr. Tongue's 
familiarity with the instruments and his conscientious devotion to 
the scientific work of the ship combined to make his calculations 
reliable within a comparatively small limit of personal error. 

In addition to surface specimens, samples of water were, so far 
as possible, taken at the same time from the circulating pump the 
intake of which is about four feet below the surface. This water 
was drawn from the tap in the laboratory, enough water being first 
allowed to run off entirely to clear the pipe from the laboratory to 
the sea. It was not believed that the modification of the water on 
its passage through this pipe, which was constantly in use, could be 
sufficient to be detected by the method used in the determination of 
the specific gravities. 

Many of the salinity determinations taken at the surface during 
this cruise are included, without correction or comment, in the dredg- 
ing and hydrographic records of the cruise (Bureau of Fisheries 
Document No. 621, 1907, pp. 1-50). It was necessary in distributing 
our zoological material for study to provide each of our collaborators 
at the same time with the data of each dredge haul. Immediately 
upon our return to San Francisco, therefore, Mr. Tongue compiled 
these records from our undigested notes taken at sea. 

THE LIMITS OF ERROR IN THE OBSERVATIONS 
There were fifty observations taken on the water from the circu- 
lating pump; in three instances these readings were identical with 
those taken from water dipped from the surface (Nos. 24, 64 and 
73) ; in twenty-four instances they were greater, as follows: 

No. i: 
(No. 9: 

No. 18: 
No. 19: 
No. 25 : 
No. 27: 
No. 28: 



No. 29 : 
No. 32 : 
No. 40 : 
No. 46 : 
No. 51: 



0.00044 

0.00286) 

0.00020 

0.00003 

0.00006 

0.00018 

0.00023 

0.00003 

0.00014 

0.00009 

0.00005 

0.00003 



No. 


57: 


0.00005 


No. 


60: 


0.00030 


No. 


62: 


O.OOOIO 


No. 


66: 


0.00016 


No. 


81: 


0.00003 


No. 


91: 


0.00004 


No. 


93: 


0.00008 


No. 


94: 


0.00056 


No. 


97: 


0.00092 


(No. 


99: 


0.00207 ) 


No. 


124: 


0.00008 


No. 


129: 


0.00021 



and in twenty-three instances less, as follows 



NO. 13 SALINITY OF PACIFIC SURFACE WATER — CLARK 



No. 2: 


0.00042 


No. 


42 


O.OOOII 


No. 4: 


0.00030 


No. 


43 


0.00015 


(No. 5: 


0.00119) 


No. 


50 


0.00003 


No. 7: 


0.00035 


No. 


61 


0.00005 


No. 10: 


0.00041 


No. 


72 


0.00016 


No. II : 


0.00065 


No. 


83 


O.OOOIO 


(No. 12: 


0.00385) 


No. 


84 


0.00006 


No. 13: 


0.00023 


No. 


86 


0.00006 


No. 22 : 


0.00019 


No. 


92 


0.00019 


No. 30: 


0.00009 


No. 


no 


0.00023 


No. 41 : 


0.00041 

No. 120 : 


No. 
0.00018 


115 


0.00038 



In the cases in which the reading from the circulating pump was 
greater than that from the surface water (excluding No. 9 in which 
the surface reading, from rain or some other cause, is obviously 
abnormally low ; and No. 99 in which the reading from the circu- 
lating pump, probably because of evaporation, is obviously too high) 
we find a variation between 0.00092 (No. 97) and 0.00003 (Nos. 19, 
29, 51 and 81), with a mean of 0.00018. 

In the cases in which the reading from the circulating pump was 
less than that from the surface water (excluding Nos. 5 and 12 in 
which the surface reading is obviously too high) we find a variation 
between 0.00065 (No. 11) and 0.00003 (No. 50), with a mean of 
0.00022. 

The fact that the variation was plus in twenty-four instances and 
minus in twenty-three with no variation in three, that there is no cor- 
relation between the variation and the latitude, and that the average 
of all the variation (+0.00018 — 0.00022) is —0.00004, a quantity 
altogether too small to be detected by the instruments used, shows 
that in reality the diiTerence in the water at the surface and a few 
feet below it is entirely negligible, not falling within the scope of pos- 
sible detection by the instruments used. 

This being so we have a personal and fortuitous error of 
0.00018 + 0.00022 = 0.00040 to take into consideration so that, 
under the best of conditions we must admit of a possible variation 
of ±0.00020 from the truth. This shows graphically the absolute 
insignificance of the figures in the fifth decimal place and their entire 
dependence upon chance. 



THE REJECTION OF INACCURATE READINGS. 

Assuming that the readings from the surface and from the circu- 
lating pump are, so far as lies within the power of our instruments 
to detect, the same, we are able to compare the two readings and in 



SMITHSONIAN MISCELLANEOUS COLLECTIONS 



VOL. 60 



many cases to reject one of them as probably less accurate than the 
other. Where two readings were taken those which are probably 
the most nearly correct are (discarding the insignificant fifth deci- 
mal) as follows : 



No. I 


: 1. 0212 


No. 


50: 


1.0253 


No. 2 


: 1.0257 


No. 


51: 


1.0253 


No. 4 


: 1.0259 


No. 


57: 


1.0253 


No. 5 


: 1.0256 


No. 


60: 


1.0254 


No. 7 


1.0257 


No. 


61: 


1.0253 


No. 9 


• 1. 025 1 


No. 


62: 


1.0253 


No. 10 


: 1.0252 


No. 


64: 


1.0253 


No. II 


• 1.0218 


No. 


66: 


1.0253 


No. 12 


1.0252 


No. 


72: 


1.0252 


No. 13 


1.0243 


No. 


73-' 


1.0252 


No. 18 


1.0244 


No. 


81: 


1.0248 


No. 19 


1.0250 


No. 


83: 


1.0251 


No. 22 


1.0250 


No. 


84: 


1.0252 


No. 24 : 


1.0250 


No. 


86: 


1.0253 


No. 25 


1.0250 


No. 


91: 


1.0253 


No. 27 


1.0254 


No. 


92: 


1.0253 


No. 28 


1.0253 


No. 


93: 


1.0253 


No. 29 


1.0252 


No. 


94: 


1.0254 


No. 30 : 


1.0252 


No. 


97: 


1.0260 


No. 32 : 


1.0247 


No. 


99: 


1.0263 


No. 40 : 


1.0253 


No. 


no: 


1. 0261 


No. 41 : 


1.0254 


No. 


115: 


1. 0261 


No. 42 : 


1.0254 


No. 


120: 


1.0257 


No. 43 : 


1.0253 


No. 


124: 


1.0258 


No. 46: 


1.0253 


No. 


129: 


1.0260 



CALCULATION OF THE CONSTANT REPRESENTING THE 
INSTRUMENTAL ERROR 

During the cruise of the " Albatross " among the Philippine Islands 
two hundred and twent3^-one observations of the surface density 
were taken, with the instruments which I myself had used in 1906 ; 
these observations show considerable variation, but the average is 

I-024533- 

There were also taken on the same cruise eighty observations of 
the salinity below 100 fathoms ; these Hkewise exhibit a considerable 
amount of variation, and give an average of 1.025048. 

The records for the eighty-four observations taken among the 
Philippine Islands below the surface are in detail as follows: 



NO. 13 SALINITY OF PACIFIC SURFACE 



34 fms 


. 1.02386 


50 '•■ 


1.02523 


78 " 


1.02516 


96 " 


1-02551 


102 " 


1.0245 1 


105 " 


1.02496 


108 " 


1.02476 


118 " 


1.02496 


122 " 


1.02526 


140 " 


1.02482 


148 " 


1.02597 


148 " 


1.02506 


150 '' 


1.02513 


150 " 


i.o2sr.'? 


■ 155 " 


1.02509 


159 " 


1. 025 1 7 


162 " 


I.O?y\?l 


170 " 


1.02489 


172 " 


1.02359 


173 " 


1.02468 


174 " 


I.O2513 


177 " 


1.02496 


178 " 


1.02523 


178 '' 


1.02496 


180 " 


I.O25IO 


186 " 


1.025 10 


191 " 


1.02489 


193 " 


I.02517 


193 " 


1.02467 


195 " 


1.02447 


198 " 


1.02468 


201 " 


1.02538 


208 " 


1.02456 


212 " 


1.02593 


214 " 


1.02354 


215 " 


1.02465 


218 " 


1.02485 


218 " 


1.02468 


220 " 


1.02509 


220 " 


1.02500 


224 " 


1.02525 


225 " 


1.02492 


averages are : 


o-ioo fms. 1.02494 


100-150 


" 1.02505 


150-200 


" 1.02482 


200-250 


" 1.02487 


250-300 


" 1.02480 


300-350 


" 1.02494 



WATER 


—CLARK 


230 fms. 


1.02496 


231 " 


I.O2513 


234 " 


1.02484 


244 " 


1.02482 


248 " 


1.02517 


249 " 


1.02482 


258 " 


I.02516 


265 " 


1.02430 


272 " 


I.02/12I 


280 " 


I.O2517 


295 " 


1.02482 


299 " 


1.02502 


300 " 


1.02495 


310 " 


1.02543 


312 " 


1.02484 


340 " 


1.02454 


375 " 


1.02576 


379 " 


1. 02521 


380 '' 


1.02459 


393 " 


1.02480 


394 " 


1.02468 


411 " 


1.02475 


422 « 


1.02566 


450 " 


1.02556 


494 " 


1.02522 


502 " 


1. 02457 


515 " 


1.02523 


524 '' 


1.02538 


525 " 


1.02577 


530 " 


1.02467 


554 " 


1.02497 


564 " 


1.02533 


565 " 


1.02505 


584 " 


1.02535 


604 " 


1. 02441 


612 " 


1.02516 


638 " 


1.02492 


730 " 


1.02564 


745 " 


1.02548 


775 " 


1.02606 


958 " 


1.02516 


1804 " 


1.02574 



350- 400 fms. 1. 02501 
400- 450 " 1.02532 
450- 500 " 1.02522 
500- 600 " 1. 025 14 
600- 700 " 1.02483 
700-1804 " 1. 0256 1 



8 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 6o 

Comparing the known average density of the surface water of the 
Philippine archipelago, about 1.02675, "^i^h the average of the ob- 
servations taken by the " Albatross," 1.02453, we find the latter to be 
0.00222 too low. Possibly part of the difference is due to the excess 
of salinities taken near the shore in the '' Albatross " records. 

Comparing the known average density of the deep water of the 
Pacific, 1.02650, with the average of the eighty observations taken 
by the ''Albatross " below 100 fathoms, 1.025048, we find the latter 
to be 0.00145 too low. A glance at the records suggests that the 
difference really is somewhat greater, for the water bottles evidently 
did not always contain water from the depth to which they were sub- 
merged. 

A similar comparison of the densities as given by Makaroff, and 
as determined by myself in the same localities at six well separated 
places show my observations as calculated to be too low by 0.00136, 
0.00184, 0.00215, 0.00210, 0.00115 and 0.00175. 

If we average these differences between the observations taken on 
the " Albatross " and those taken by the British, German, Swedish 
and Russian ships we will get a correction which, when applied to the 
former, will make them comparable to the latter, or at any rate 
nearly enough so for the purposes of the present study. The average 
of these eight differences is 0.00175, which is the correction which 
will be used throughout this paper. The average of my six obser- 
vations which are comparable to those of Makaroff*, all of which were 
calculated by the same observer, is 0.00173. 

On plotting my observations, corrected b}^ comparison with the 
determinations of Makaroff on the western side of the Pacific upon 
a chart, I found that one of my stations was almost on the exact 
spot occupied by a station recorded by Lenz, in the Gulf of Alaska, 
and I was gratified to find that the salinity given by Lenz, and my 
own determination of the salinity with the empirical correction 
added, were identical. 

It will be noticed that all of the salinity records published by 
Mr. Alexander Agassiz for the mid-Pacific region which were taken 
on board the '' Albatross " are in need of about the same correction 
to make them comparable with those of the ships of other nations. 

The necessity for this correction arises from the fact that the 
instruments were not standardized before being used. 



NO. 13 SALINITY OF PACIFIC SURFACE WATER — CLARK 9 

BRIEF RESUME OF THE CONDITIONS FOUND IN THE 
NORTH PACIFIC 

For our knowledge of the water densities and of the temperatures 
of the North Pacific we are chiefly indebted to the late Vice- Admiral 
S. O. Makaroff of the Russian Navy. Not only did he take an 
enormous number of observations of his own, beginning in 1866 as a 
naval cadet and from that time almost constantly until his death 
on the *' Variag," but in an exhaustive monograph published in 
1894/ he summarized and digested all the work of the others who 
had taken observations in that area, republishing, often with certain 
corrections calculated by himself, all their data. 

The following account' of the conditions in the Pacific is chiefly a 
summary of that given by Makaroff. 

Speaking broadly, there is found in the trade wind belt of the 
western part of the Pacific, a zone of warm water with a high salin- 
ity; water with a density of more than 1.0270 is only found in this 
zone and along the equator ; beyond this area as far as the Philippines 
and Japan, and approaching the equator in a broad curve around it 
to the eastward, we find water having a density of from 1.0265 to 
1.0270. Corresponding to latitude 42° to 46° N. we find water with 
a density of from 1.0255 to 1.0260; this approaches the coast of 
California where it mingles with the coast water and, taking a direc- 
tion toward the southsouthwest, forms a cuneiform area within the 
area of water of higher salinity. It is probable that this area of low 
salinity (which hes to the southward of the Hawaiian Islands) is nar- 
rower in August than in March, and also that it is then situated more 
to the southward. This zone corresponds to the so-called California 
current. 

The surface water to the northward of the zone with density 
ranging from 1.0255 to 1.0260 has a density of from 1.0250 to 1.0255, 
and Makaroff believed it probable that the larger part of the surface 
water of the Bering Sea lies within these extremes (see beyond, 
p. 17). 

The mean specific gravity of the surface water of the Pacific 
(excluding the enclosed seas) is 1.0264. 

The specific gravity of the lower levels over the entire Pacific 
is everywhere the same ; the average is 1.0265. 

The " Challenger " found near the antarctic ice at 50 fathoms a 
specific gravity of 1.0265, or the same as the mean for the deep water 

^ " Vitiaz " i Tikhii Okean ; Le " Vitiaz " et I'Ocean Pacifique. St. 
Petersbourg, 1894. 



lO SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 6o 

of the Pacific ; Makaroff believes that the water of the deeper layers 
in the Pacific comes originally from the Antarctic Ocean, an hypo- 
thesis which finds much support in the zoogeography of the Pacific 
region. 

The specific gravity of the water of the Philippines and of the 
Sulu and Celebes Seas is much less than that of the adjacent parts of 
the Pacific. 

In order to appreciate the significance of the varying salinities 
in the North Pacific and in the enclosed seas bordering upon it some 
attention must be given to the circulation of the water in the region 
and to the course and interrelationships of the various currents found 
there. 

The largest of these currents, and by far the most important, is 
the warm current from the south carrying water of high salinity, 
known as the Kuro-Siwo or Japanese current, and corresponding in 
a general way to the so-called Gulf Stream of the western Atlantic, 
On reaching the coasts of Japan and the peninsula of Korea the 
Kuro-Siwo divides into three parts ; the principal part advances 
along the southern coast of Japan ; the second enters the Sea of 
Japan through the straits of Korea and forms the so-called Tsu- 
shima current; the third turns to the westward and resembles in its 
general characteristics a similar branch which is given off from the 
Kuro-Siwo south of Formosa. It is not yet definitely known just 
what direction this branch takes ; but as Makaroff found in running 
from the Chu-San archipelago to Nagasaki a water with a very 
high specific gravity it seems probable that this branch, after de- 
scribing a broad curve, turns toward the south in the same manner 
as does the branch given off south of Formosa. 

The Tsu-Shima current does not occupy the entire width of the 
Korean Straits, for there is a zone of cold water with a low specific 
gravity along the Korean Coast which is part of a similar zone 
occupying the entire western part of the sea of Japan. On entering 
the Sea of Japan through the Korean Straits the Tsu-Shima current 
turns to the right and runs northeastward along the Japanese coast. 
It is probable that this current influences the salinity of the entire 
southeastern part of the Sea of Japan. 

Observations have shown that near Dajelet Island at a depth of 
lOO meters the cold water is sharply separated from the warm water 
which here is shoved downward, forming a deep current beneath 
the superficial water of low salinity flowing southward from the 
north. 



NO. 13 SALINITY OF PACIFIC SURFACE WATER — CLARK II 

The Tsu-Shima current, advancing toward the northeast, reaches 
the Strait of Tsugarii, through which a large amount of water flows 
to the eastward from the Sea of Japan to the Pacific. Continuing 
further toward the northeast the greater part of what remains of 
the Tsu-Shima current flows through the Strait of La Perouse into 
the Sea of Okhotsk, and a comparatively small portion continues 
northward along the west coast of Sakhalin. 

The salinity of the surface water in the Strait of La Perouse is 
greatly diminished by an admixture of fresh water from rain and 
snow, but at depths greater than 25 meters it is found to be the same 
as that of the water passing through the Korean Strait. 

The principal branch of' the Kuro-Siwo which follows the southern 
coast of Japan passes with great swiftness through van Dieman 
Strait, and thence runs parallel to the coast only touching the extremi- 
ties of the capes which extend furthest outward from the southern 
shore, Siwo-Misaki, Kawatsu, etc. It does not enter any of the gulfs 
or bays. In winter its limits are readily recognized by the high tem- 
perature and the high specific gravity, but in summer they can be 
determined only by the latter. 

The salinity of the water of the Inland Sea is much less than that 
of the neighboring parts of the Pacific or of the Sea of Japan ; Maka- 
roff found it to be in January 1.02527, in May 1.02544 and in June 
1.02632, the average being 1.0252; the ''Challenger" found the 
average salinity of the eastern part in May to be 1.02375. 

The Kuro-Siwo only follows the coast of Japan as far as Cape 
Inaboie Saki, at that point turning to the east. Many observations 
made on vessels running between Kamchatka and Japan have proved 
that in the later summer months the warm water extends much 
further to the northward than the parallel of Cape Inaboie Saki 
though, judging from the specific gravities, the northern limit of the 
Kuro-Siwo scarcely passes 40° N. At that latitude the surface water 
of the Kuro-Siwo turns to the eastward, and has a specific gravity 
of less than 1.0260. However, water with a specific gravity of 
1.0260 is found in the deeps of the Bering Sea and reaches to within 
200 meters of the surface. It is to be noticed that in the Bering Sea 
the isotherms rise toward the east, so that we are justified in believing 
that the warm water approaches nearer the surface in the eastern than 
in the western part. 

In the Sea of Japan the heavy water, which is borne by the Tsu- 
Shima current, turns to the eastward ; but it does not at all points 
touch the island of Nipon as it is deflected by a moderately strong 



12 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 6o 

current of sniall salinity which comes from the Inland Sea, entering- 
the Sea of Japan by the Straits of Shimonoseki. This heavy water 
in flowing northward along' the coasts of Nipon, Yezo and Sakhalin 
very gradually becomes less and less saline. 

Near the Siberian coast, water with a specific gravity of from 
1.0250 to 1.0255 descends from north to south, washing the whole 
coast of the western part of the Sea of Japan and making itself felt 
even in the Korean Strait. 

The specific gravity of the water in the Sea of Japan is higher than 
that in corresponding latitudes in the Pacific ; in going from Hako- 
date to Vladivostok the specific gravity diminishes rapidly west of 
134° and near Vladivostok is about o.ooii less than in the Strait of 
Tsugaru. 

The mean specific gravity of the water of the Sea of Japan, both 
at the surface and in the deeper portions, is 1.0260. 

Tracing a line from the Bay of St. Olga to the middle of the 
Korean Strait we find that in the western part the specific gravity, 
both at the surface and below, does not pass 1.0260. The heavy 
water which enters the Strait of Korea occupies in width more than 
half the strait, and its entire depth ; further northward, however, the 
thickness of the heavy layer does not exceed 100 meters. Water 
with a specific gravity of more than 1.0262 is only found in the 
eastern part of the sea. 

The Strait of La Perouse includes two zones of water of different 
salinities and temperatures. In the southern part there is a warm 
current which descends toward the east near the coast of Yezo, and 
in the northern part, near the coast of Sakhalin, there is a cold current 
running toward the westward out of the Sea of Okhotsk. The line 
of separation between these two currents is not vertical but strongly 
inclined; the water from the Sea of Okhotsk, lighter and colder, 
advances in a mass having a cuneiform section over the warmer, 
but also heavier, water of the eastern part of the Sea of Japan which 
passes downward and, turning to the right on account of the rota- 
tion of the earth, extends far toward the northeast under the cold 
water. This water from the Sea of Japan has a specific gravity of 
1.0260, and a temperature of ig°C. in August; it is probable that in 
winter the temperature does not fall below 3° C. 

The surface water of Aniva Bay, in southern Sakhalin, has a 
specific gravity of 1.0245; for a while in August its temperature 
may be as much as 17° C, but the rest of the year it is much lower. 



NO. 13 SALINITY OF PACIFIC SURFACE WATER — CLARK 1 3 

Under the upper layer of comparatively warm water is a cold layer 
with a specific gravity of 1.0254. 

On account of the quantity of water which flows through the 
Korean Strait and raises the surface of the Sea of Japan and that 
of the Gulf of Tartary above that of the surrounding seas the bulk 
of the water from the x\mur River, instead of turning to the right 
and flowing to the southward as would naturally be expected, turns 
to the north, though part of it comes southward along the western 
shore of the Gulf of Tartary where it causes a considerable dimi- 
nution of the salinity. In this gulf the water of the lower layers 
near Sakhalin, below 40 meters, has a higher specific gravity than 
that near the continent. In the upper layers there is no regularity 
in the variations so that they are probably the result of the action 
of winds, local currents, tides, etc. 

Almost the entire central portion of the Sea of Okhotsk has a 
specific gravity between 1.0245 and 1.0250; near the coasts the 
water is in general less saline. In the Bay of Oudsk and near Sak- 
halin the specific gravity is less than 1.0230, showing the influence 
of small rivers which empty into the southwestern part of the Sea 
of Okhotsk, and especially of the Amur. Krusenshtern found near 
the northern end of Sakhalin water with a specific gravity of 1.0130. 

The deeper water of the Sea of Okhotsk is more dense than that 
nearer the surface ; at a depth of 800 meters it has a specific gravity 
of 1. 0261, or the same as that of the water which enters through the 
Strait of La Perouse. As in the Bering Sea this lower stratum of 
warm water with high salinity is found at a greater depth in the 
west than in the east, for in both seas there is, along the western 
coast, a cold current of low salinity which submerges to a great 
depth the warm water with high salinity. Makaroff believed that the 
water of the Sea of Okhotsk enters that sea by way of the Strait 
of La Perouse and not from the Pacific. 

The mean density of the water of the Sea of Okhotsk and of all 
its bays is 1.0242. 

Among the Kuril Islands the surface water is mixed with heavier 
and much colder water than that occurring on the coast of Kam- 
chatka, the greatest degrees of salinity and cold being midway 
between Kamchatka and Japan and not at the northern end of the 
chain ; this heavy and cold water forms a broader belt on the Pacific 
than on the Okhotsk Sea side of the islands ; it was supposed by 
Makaroff to be in reality water from the great depths of the Okhotsk 



14 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 6o 

Sea which is here forced to the surface through the pressure of the 
deep current of warm heavy water which enters the Okhotsk Sea 
through the Strait of La Perouse. It may be, however, that this 
explanation is not quite correct, and that the presence of this abyssal 
water among the Kuril Islands is to be accounted for rather by the 
application of Ekmann's hypothesis. 

Relatively warm water with a specific gravity of 1.0260 is found 
in the depths of the Bering Sea, reaching to within 200 meters of 
the surface ; it is found much nearer the surface at the Commander 
Islands than along the coast of Kamchatka, a phenomenon similar 
to that observed in the Sea of Okhotsk. It is to be remarked that 
in the Bering Sea the isotherms rise toward the eastward as one 
leaves the Kamchatkan coast so that we are justified in believing that 
the warm water approaches nearer the surface in the eastern part 
than in the western, though there is no evidence that the specific 
gravity is higher in the former. 

The layer of warm surface water along the coast of Kamchatka is 
very shallow, and observations on this coast prove the existence 
of an intermediate zone of cold water, just as in the western part 
of the Sea of Okhotsk ; determinations made in latitude 6o°-62° N. 
show that the specific gravity is still low at a depth of 150 meters 
which induces us to suppose that here the water is influenced by the 
water of the Arctic Ocean and is not directly connected with the 
warm water of the more southern latitudes. 

At Port Clarence, Alaska, the specific gravity of the deeper water 
is from 1.0136 to 1.02 16, much less than in the middle of the Bering 
Strait or in the Arctic Ocean. The " Vega," on her course across 
the Bering Strait from Port Clarence to Simavine, found that the 
specific gravity rose a little, the value being the same from the 
surface to the bottom; beyond longitude 171° W. the specific gravity 
of the surface water became much less than that of the deeper layers, 
while the temperature was also lower at all depths. 

In the Bering Strait the more saline water occurs on the western 
side ; the comparatively warm water which enters the Arctic 
Ocean on the eastern side is strongly mixed with the water from the 
Alaskan rivers and shows no trace at any depth of the water of the 
Kuro-Siwo which apparently does not reach this point. 

Observations made near the coast of Asia in latitude 63° 16' N. 
showed the presence of an intermediate layer of cold water similar 
to that observed near the coast of Kamchatka. 



NO. 13 SALINITY OF PACIFIC SURFACE WATER — CLARK 1 5 

A water of low salinity descends to the southward near the coast of 
Kamchatka, and apparently continues down the Kuril chain ; further 
from the coast the water of the Bering Sea has a salinity of about 
1.0250, corresponding to the latitude. 

METEOROLOGICAL CONDITIONS TENDING TO LOWER THE 
COMPARATIVE SALINITY OF THE PACIFIC 

Professor Kriimmel has shown that the Pacific is less saline than 
the Atlantic, the difference between them being comparatively slight 
in the southern hemisphere, but very considerable in the northern. 
A preliminary examination of the data available for the portion of 
the north Pacific north of Puget Sound shows that the low salinity 
of this area is much more marked on the eastern than on the western 
side. Professor Woekoff has explained the increased salinity of the 
Atlantic by the constant loss of water from the Atlantic and from the 
Atlantic water sheds through the operation of constant westerly 
winds which, passing across Europe, Asia and Africa, charged with 
Atlantic water, deposit it in the interior basins of those continents 
which have no connection with the oceans, and even in the Asiatic 
water shed of the Pacific itself. The Pacific loses no water in this 
way on account of the high mountains which form an almost unbroken 
barrier along its eastern shores. 

THE SEASONAL VARIATION IN THE SALINITY OF THE WATER 
OFF THE CALIFORNIAN COAST 

A preliminary examination of the salinity records obtained by the 
'' Albatross " off the Californian coast, with the necessary corrections 
applied, shows a most interesting condition. In the summer the 
isoh alines, upon reaching the vicinity of the Californian coast, bend 
abruptly to the northward and run more or less parallel with the 
shore, this effect being noticeable nearly to Puget Sound. In the 
winter this distortion of the isohalines disappears, and they then run 
to the coast almost exactly along the parallels of latitude. 

Dr. Thorade has worked out in great detail the seasonal variation 
in temperature for the Californian coast, and he finds that the iso- 
therms near the coast bend downward and run far to the southward 
in summer, but become more or less coincident with the parallels of 
latitude in winter. He has explained the phenomenon as resulting 
from the upwelling of abyssal water along the Californian coast in 
summer, this upwelling decreasing and practically disappearing in 



l6 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 6o 

winter. His explanation of the coldness of the coast strip as a result 
of the up welling of abyssal water presumes that this cold water 
should also be exceptionally saline, and therefore that the isohalines 
should bend abruptly to the northward just as the isotherms bend 
abruptly to the southward, while in the winter both isotherms and 
isohalines should follow courses more nearly agreeing with the paral- 
lels of the latitude. My observations on the seasonal variations in 
the salinity of this coast agree absolutely with his on the temperature. 

The charts published by Makaroff show that in the mid-Pacific, 
between 170° and 180° W. long, the mean isohaline of 1.0255 ^^^s 
approximately along the 46th parallel, and the isohaline of 1.0260 
is approximately in 42° 50' N. ; the 1.0250 isohahne is far up in the 
Gulf of Alaska where it runs parallel to the coast, crossing the merid- 
ian of 140° W. in about 56° N. From these positions there is a 
slight southerly movement in winter, and in a corresponding north- 
erlv movement in summer. 

In the summer the isohaline of 1.0250, running in a generally south- 
erly direction, turns northward at about 42° 15' N. lat., 127° W. long., 
joining the coast of Cape Moares, in 45° 30' N. lat. The isohaline 
of 1.0255 turns northward at 37° N. lat., 127° W. long., and runs 
thence almost directly north between the meridians of 125° 30' W. 
and 125° 00' W. (practically coinciding with the latter north of 
41° N. lat.) for a considerable distance, eventually turning eastward 
and reaching the coast at Cape Blanco. The isohaline of 1.0257 
rises in a broad curve from 34° 40' N, lat., 133° W. long, to 36° 30' 
N. lat., 123° 30' W. long., and then turns rather abruptly northward 
and northwestward, running parallel to the coast to 39° N., when it 
gradually turns northward again, reaching the coast at Cape Alendo- 
cino. The noticeable feature of this isohaline is the broad seaward 
bend which, considered in its relation to the coast line, reaches its 
maximum in the latitude of San Francisco, and its actual maximum 
westerly extension in 39° N. lat. In the San Francisco region there 
is a small area with a salinity of less than 1.0255 bounded by a curve 
of large radius extending from Point Arena (just south of 39° N. 
lat.) on the north to Pescadero Point (about 37° 15' N. lat.) on the 
south. This curve crosses 38° N. in 123° 30' W., and 123° W. in 
37° 30' N., its course being almost parallel to that of the 1.0257 line 
further oflf shore. The isohaline of 1.0260 turns northward at 33° 
N., 125° W., and runs in a broad curve northnortheast to Monterey 
Bay. 



NO. 13 SALINITY OF PACIFIC SURFACE WATER CLARK 1 7 

In the winter the isohahnes east of 133° W. run approximately 
along the parallels of latitude, rising only slightly near the coast ; 
the isohaline of 1.0255 rises from 33° 50' N. lat., 124° W. long to 
Point Sal, north of Point Conception; the isohaline of 1.0257 ^^^"S 
from 33° N. 123° W. to Santa Barbara; and the isohaline of 1.0260 
rim from 32° 20' N. 121° W. to Encinitas, just north of San Diego. 

THE BERING SEA 

A preliminary examination of the American records available for 
the Bering Sea shows a rather interesting condition, though one 
which is essentially what would be predicated from a survey of the 
land and submarine contours and of the drainage systems. 

]\Iakaroff showed the isohaline of 1.0250 running from 45° N. 
lat. 150^^ E. long, nearly in a straight line (with a slight regular con- 
vexity toward the east) to Bering Island, then turning more to the 
eastward and running (again with a slight convexity toward the 
southeast) to about lat. 61° N., long. 180° WE.; from this point 
he was unable to trace it further owing to an absence of data. It 
appears from the records at hand that here it turns abruptly to the 
southward running as far as lat. 55° N. which it crosses in long. 
179° 20' W., then making a broad sweep toward the east, crossing 
lat. 54° N. at long. 177° 30' W., reaching lat. 53° 35' N. in long. 
174° 30' W., and, continuing the same curve, crossing lat. 55° N. 
again in long. 171° 25' W. ; here it turns abruptly toward the NNW., 
crossing lat. 55° N. in long. 171° 55' W., and reaching lat. 55° 50' 
in long. 171° 55' W., curving sharply about and coming southward 
again in a course parallel to that taken going north and about thirty 
miles to the eastward (forming a long narrow finger toward the 
NNW., lying chiefly between long. 171° W. and long. 172° W\) 
as far as lat. 54° 25' N. long. 170° 30' W. where it gradually turns 
eastward, after long. 169° W. running between lat. 54° 05' N, and 
lat. 54° 10' N. to long. 167° 05' W. where it turns abruptly south 
and then west, running WSW. nearly in a straight Hne to Uliaga in the 
Islands of Four Mountains. 

W^e thus see that the water with a specific gravity of 1.0250 or 
more is entirely confined to that part of the Bering Sea west of long. 
167° W., while except for a narrow strip just north of the Andreanof 
Islands, the Islands of Four Mountains, Umnak and western Un- 
alaska, it Hes to the west of long. 179°. It therefore lies entirely in the 



l8 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 6o 

deep western part of the sea, its southeastern extremity showing a 
curious approximate coincidence with the looo fathom hne. 

The westerly position of this water of comparatively high salinity 
which enters the Bering Sea from the southward is evidently gov- 
erned by the breadth and depth of the channels. Between Kamchatka 
and the Commander Islands it lies beneath the colder and less saline 
water flowing southward along the Kamchatkan coast, this super- 
ficial layer progressively decreasing in thickness toward the east and 
allowing the heavier and warmer water to reach the surface at Bering 
Island. The broad deep channel between the Commander and 
western Aleutian Islands allows of the passage of great quantities 
of Pacific water, but the large Andreanof Islands with the narrow 
channels between them form a barrier so that little is able to flow 
by them. Between the Andreanof Islands and Umnak, howxver, 
there are again broad open channels, inluding the Amukta Pass, 
and these allow of the passage of enough water to form to the north- 
ward the long finger above described, and the somewhat similar 
finger stretching toward the east nearly to long. 167° W. 

The general configuration of the area of high salinity in the 
western part of the Bering Sea suggests that it is not a constant, 
but rather an intermittent flow, for were it constant, one would scarcely 
expect to find it extending itself by such long and narrow processes as 
occur north, and again east, of the Amukta Pass, or faihng to reach 
the shores of islands upon which the precipitation is not by any 
means sufficient to keep it away. 

It is quite possible that we have in the Bering Sea a condition 
comparable to that shown by Cleve, Ekmann and Pettersson to exist 
in the Norwegian Sea, and that there is a yearly pulsation due to 
a variation in the height of the level of the north Pacific, reaching 
the maximum in November and the minimum in March, by which 
the flowing of the surface water of the Pacific through the Aleutian 
channels is increased during the late spring, summer and early 
autumn, decreasing in the winter and early spring. While the flow 
of water of comparatively high salinity from the Pacific into the 
Bering Sea is undoubtedly constant, and toward the western part of 
the sea always strong, its eastward extension is probably governed 
by an annual variation, expanding and contracting with more or less 
regularity. 

Toward the eastern part of the Bering Sea the density decreases 
very slowly; the 1.0240 line crosses long. 164° W. in lat. 57° 30' N., 



NO. 13 SALINITY OF PACIFIC SURFACE WATER — CLARK I9 

running- toward the southeast; crossing long. 163° W. in lat. 55° 15' 
N. it turns south running to a point fifteen miles north of Point Blaine 
on the Alaska peninsula, then turns southwest and follows the coast 
to Cape Mordvinof on Unimak where it reaches its southwestern 
limit. 

South of the Alaska peninsula the 1.0250 line runs in a northeast- 
southwest direction slightly to the northwest of lat. 54° N. long. 
158° W. 



SYNOPSIS OF THE SALINITIES OBSERVED DURING THE 1906 
CRUISE OF THE " ALBATROSS " 

Locality 0^^--a- ^^^^.^^ 

Near San Francisco Bay (i) 1.0212 

From San Francisco to the Columbia River (2-10) 1.0255 

Off the Columbia River (11) 1.0218 

Off Clearwater, Washington (12) 1.0252 

Strait of Juan de Fuca (13) 1.0243 

At Tacoma (14) 1.0211 

Strait of Georgia (15) 1.0214 

Union Bay, Vancouver Island (16-17) 1.0221 

Queen Charlotte Sound ( 18) 1.0224 

Provost 1. to long. 145° W ( 19-26) 1.0250 

Long. 145° W. to long. 158° W (27-30) 1.0253 

South of the Shumagin Is (31) 1.0240 

Eastern end of the Aleutian Is (32-33) 1.0247 

Near Bogosloff ■ (34) 1.0250 

Unimak to Seguam (35-38) 1.02525 

Atka to Semisopochnoi (39-42) 1.0254 

South Central Bering Sea (43-52) 1.0253 

Vicinity of Semisopochnoi Is (53-55) 1.0254 

South of Amchitka (56) 1.0250 

Kyska to Copper (Myedni) Island (57-68) 1.0253 

Copper I. to and about Bering I (69-76) 1.0252 

Between Bering I. and Kamchatka (77-78) 1.0250 

Near Starichkof I (79-8o) 1.0246 

Off Cape Asacha, Kamchatka (81) 1.0248 

About southern Kamchatka (82-86) 1.0252 

Vicinity of Simushir, Kurils (87-90) 1.0255 

Urupp, Kurils, to Cape Yerimo, Yezo (91-95) 1-0253 

Strait of Tsugaru ^ (96) 1.0255 

Eastern part of the Sea of Japan (97-104) 1.0260 



20 SMITHSONIAN MISCELLAS^EOUS COLLECTIONS VOL. 6o 

Locality Observa- p^^,,^ 

Toyama Bay (1.0216-1.0261) (105-114) 1.0253 

Near Waijima (115) 1.0261 

Komatsu to Kioga Saki (116-124) 1.0256 

Oki Is (125-126) 1.0255 

Between Oki Is. and Hornet I. (Liancourt Rocks) (127) 1.0252 

Between Oki Is. and Hornet I (128) 1.0258 

South of Hornet L and iMatsushima I (129-131) 1.0261 

Coast of Korea, and the Korean Straits to Tsu-Shima and 

Ikki-Shima (132-139) 1.0248 

South of Hirado I. and near Nagasaki (140-141) 1.0253 

South of Goto Is (142) 1.0252 

South of Goto Is. and West of Koshiki I (143-148) 1.0247 

West of Uji-Shima and South of Kusakaki-Shima (149-151) 1.0252 

South of Tanega-Shima (152-153) 1.0262 

West of Tanega-Shima ( 154) 1.0257 

Off Kagoshima Gulf (i55) 1.0251 

In Kagoshima Gulf (156) 1.0239 

Van Dieman Strait, and eastward to the Inland Sea (157-162) 1.0261 

Inland Sea (163-164) 1.0241 

South of the Kii Channel (165) 1.0259 

In Oshima-Ko ( 166) 1.0238 

Off Oshima-Ko and South of Hamamatsu (167-172) 1.0257 

Near No-Shima (i73) 1.0259 

Northeast of Choshi ( 174) 1.0254 

From Choshi to Tsugaru Strait (175-179) 1.0255 

From Iwanai Bay to Rebunshiri I., and west of Southern 

Sakhalin ( 180-183) 1.0258 

Eastern part of the Gulf of Tartary (184-185) 1.0256 

Aniva Bay, Sakhalin Island ( 186) 1.0245 

Near Cape Siretoko (187) 1.0243 

Southeastern Sakhalin to Cape Patience (188-191) 1.0235 

Sea of Okhotsk ( 192) 1.0239 

Sea of Okhotsk (193) 1.0245 

Sea of Okhotsk (i94) 1.0247 

Sea of Okhotsk (195) 1.0256 

Sea of Okhotsk (196) 1.0255 

South of Kunashir and Otsu Saki ( 197-198) 1.0253 

Near Cape Yerimo, Yezo ( 199) 1.0252 

Off Urakawa and west of Urakawa (200-201) 1.0258 

From southeast of Alororan to Sendai (202-204) 1.0254 

Off Sendai (205) 1.0259 

Northeast of Choshi (206) 1.0249 

Vicinity of No-Shima (207-208) 1.0255 

Suruga Gulf (209-215) 1.0250 

Off Suruga Gulf (216-218) 1.0256 

West of Nii Jima (219) 1.0254 

Sagami Bay (220-221 ) 1.0253 



NO. 13 SALINITY OF PACIFIC SURFACE WATER — CLARK 21 

NARRATIVE 
Our first observation, made not long after leaving San Francisco 
Bay, showed water of a comparatively low density (1.0212), pos- 
sibly indicating the influence of the bay water. From Marin county 
to the mouth of the Columbia River we passed through water vary- 
ing in density from 1.025 1 to 1.0259, with an average of 1.0255 ; this 
variation was probably due to our crossing closely approximated 
isohalines running more or less parallel to the shore line, though 
possibly part of it was due to the effect upon the surface water of 
the various rivers which enter the ocean along this coast. Off the 
mouth of the Columbia River the density was, as would naturally 
be expected, very low (1.0218) ; it rose to 1.0252 further north and 
fell to 1.0243 in the Straits of Fuca. 

At Tacoma, in the Straits of Georgia, and at Union Bay, Van- 
couver Island, the density was low, ranging between 1.02 11 (at Ta- 
coma) and 1. 022 1 (at Union Bay), on account of the drainage from 
the land; but in Queen Charlotte Sound we found it to be again 
about the same (1.0244) as it was in the Straits of Fuca. 

From the Queen Charlotte Sound as far as long. 145° W. the density 
was very uniform (1.0250) ; at that point a slight rise was noted 
(1.0253) which was maintained to long. 158° W., beyond which lo- 
cality, in the vicinity of the Shumagin Islands, it dropped to 1.0240, 
rising again south of the eastern end of the Aleutian chain to 1.0247. 

Near Bogosloff the density was slightly greater (1.0250), and on 
the course from Unimak to Siguam a further slight increase was 
noticed, which was augmented between Atka and Semisopochnoi. 
In the south central part of the Bering Sea the density was very 
slightly less, but on returning to the vicinity of Semisopochnoi we 
found the same figure which we had previously observed between 
Atka and Semisopochnoi. Our observation south of Amchitka is 
rather low, and may possibly be incorrect. Between Kyska and 
Copper Island the readings were the same as those in the south 
central Bering Sea (1.0253), and slightly less than those between 
Atka and Semisopochnoi. From Copper Island to and about Bering 
Island a slightly lessened density (1.0252)1 was noted, and a further 
decrease was observed between Bering Island and Kamchatka 
(T.0250). 

Near Starichkof Island a comparatively low density was found 
(1.0246), which rose off Cape Asacha (1.0248) and again about the 



22 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 6o 

southern extremity of Kamchatka where, both in the Pacific and in 
the Okhotsk Sea, it was again the same as between Copper and 
Bering Islands (1.0252). 

In the vicinity of Simushir the salinity was notably high (1.0255), 
falling again on the course between Urupp and Cape Yerimo, Yezo, 
to the same figure we had observed in the south central Bering Sea 
and between Kyska and Copper Islands (1.0253). 

In the Strait of Tsugaru the same density was observed as in 
the vicinity of Simushir (1.0255), but we found it greatly increased 
in the eastern part of the Sea of Japan (1.0260). 

In Toyama Bay we determined salinities ranging from 1.02 16 
(in the southern part) to the normal salinity for the eastern part of 
the Sea of Japan, 1.0260 (in the more northern part). Near Wai- 
jima we found the same salinity as in the same general region further 
to the north (1.0261) ; but between Komatsu and the Oki Islands it 
was considerably less (1.0256), and we noted a further drop in the 
vicinity of the Oki Islands (1.0255). 

Between the Oki Islands and Hornet Island (Liancourt Rocks), 
we determined two quite dififerent readings, 1.0252 and 1.0258, while 
south of Hornet Island and south of Matsushima we found the high 
density characteristic of the east coast of the Sea of Japan (1.0261). 

Along the Korean coast and in the Korean Strait about Tsu-Shima 
and Ikki-Shima we found water of a very low density (1.0248), which 
was the same as that previously observed off Cape Asacha, Kam- 
chatka, and in general comparable to that along the east Kamchatka 
coast. South of Hirado Island and near Nagasaki the density was 
greater (1.0253) , and was the same as that in the south central Bering 
Sea, between Kyska and Copper Islands and along the southern 
Kurils, and almost the same as that between the Oki Islands and 
Hornet Island. South of the Goto Islands and west of Koshiki 
Island (except in one spot in the former locality where we found 
a density of 1.0253, or practically the same as that south of Hirado 
Island and near Nagasaki) the density was 1.0247, or approximately 
the same as that along the Korean coast and about Tsu-Shima and 
Ikki-Shima. West of Uji-Shima and south of Kusakaki-Shima the 
density was about the same as that south of Hirado Island and near 
Nagasaki (1.0252), and the same as that about southern Kamchatka. 
South of Tanega-Shima the salinity became much higher (1.0262), 
reaching about the same figure as in the eastern portion of the Sea of 
Japan. West of Tanega-Shima it was less (1.0257), and off Kago- 



NO. 13 SALIXITY OF PACIFIC SURFACE WATER — CLARK 23 

shima Gulf much less, while within Kagoshima Gulf we found the 
water comparable to that in Toyama Bay, though only one observa- 
tion (1.0239) was taken. 

In van Dieman Strait and along- the coast to the Inland Sea the 
same density (1.0261) was found as near Waijima and generally 
in the eastern part of the Sea of Japan. 

The two observations in the Inland Sea shoAved a water of low 
salinity (1.0241) ; but south of the Kii channel we found again ap- 
proximately the same salinity as that normal for the Japanese cur- 
rent (1.0259). 

In the little land-locked harbor of Oshima-Ko the water was quite 
fresh (1.0238), while in the vicinity of that harbor and south of 
Hamamatsu we found it somewhat less saline than in the Japanese 
current (1.0257). 

Near No-Shima the salinity rose to 1.0259, ^^^ o^ oi^i* journey 
northward along the east coast of Japan to the Strait of Tsugaru 
we found the density varying between 1.0252 and 1.0258, with an 
average of 1.0255. 

In Iwanai Bay and in Ishikan Bay on the west coast of Yezo, and 
west of Rebunshiri Island and southern Sakhalin, the salinity was 
comparatively high (1.0258), dropping further to the northward in 
the eastern part of the Gulf of Tartary to 1.0256. Our single ob- 
servation in Aniva Bay in southern Sakhalin gave 1.0245, while off 
Cape Siretoko we found 1.0243. Between Cape Siretoko and Cape 
Patience the salinity varied between 1.0243 ^^^ 1.0227, the average 
being 1.0235, ^^^ ^^^ our course between Cape Patience and the 
southeastern corner of the Sea of Okhotsk it rose regularly through 
1.0239, 1.0245 and 1.0247 to 1.0256 and 1.0255, falling to 1.0253 
south of Kunashir and south of Otsu-Saki, and to 1.0252 off Cape 
Yerimo. Off Urakawa and west of Urakawa we found a salinity 
of 1.0258, southeast of Mororan to Sendai a salinity of 1.0254, while 
another observation off Sendai gave 1.0259. Northeast of Choshi 
we found a salinity of 1.0249, and in the vicinity of No-Shima a 
salinity of 1.0255. 

As was to be expected the water in Suruga Gulf proved to be. 
less saline than that of the open sea, especially in the more remote 
■portions, varying from 1.0236 to 1.0256, with an average of 1.0250; 
oft* shore in this region we found 1.0256. 

West of Nii Jima we found a saHnity of 1.0254, and in Sagami 
Bay our two observations gave 1.0253. 



24 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 6o 

AN OBSERVATION ON THE INTERMINGLING OF RIVER AND 
OCEAN WATER 

It has long been known that the water from a shallow river upon 
entering the sea spreads out fan-like over the surface of the salt 
water for a very considerable distance with little intermingling. 
While dredging one day in Suruga Gulf we had striking optical 
evidence of the truth of this. Though the day was clear there had 
been during the preceding night heavy rains over the land and the 
rivers were all swollen and very muddy. It happened that one of 
the localities in which we wished to work was within the area cov- 
ered by the extremely muddy water from a small river. The water 
was so muddy that small objects disappeared from view at a depth 
of a few inches. On hauling up the trawl a dark hole of clear black 
water was made through the muddy surface layer, which was then 
seen to be but a few feet in thickness. 

COMPARISON OF OUR FIGURES WITH THOSE PREVIOUSLY 

PUBLISHED 

xAs far as southern Kamchatka our figures agree very well with those 
of '' Vega," " Vitiaz," '' Variag " and '' Predpriatie " for the same 
region. From this point our course was through territory for which 
there are no previous records, though the " Vitiaz " established a fine 
of observations somewhat further to the eastward. We found the 
specific gravity of the water in the Kuril chain higher than would be 
expected, reaching a maximum in the middle of the group ; these com- 
paratively high figures undoubtedly represent a purely local condition, 
the result, as explained by Makaroff, of the upthrust of the abyssal 
water of the Okhotsk Sea (or of the Pacific, or of both) to the 
surface. 

About Yezo our figures again agree with those previously pub- 
lished. There are no records for the west coast of Nipon, and here 
our observations seem to indicate a belt of water of comparatively 
low salinity near the coast, probably a very thin and superficial layer 
resulting from the drainage from the land, intervening between the 
heavy water of the eastern part of the Sea of Japan and the shore 
line. 

In the region of the Korean Straits and off the Korean coast our 
figures do not quite agree with those of Makaroff, though, generally 
speaking there is but little difference ; our figures for southern and 
eastern Japan more nearly coincide with his. 



NO. 13 SALINITY OF PACIFIC SURFACE WATER — CLARK 25 

On the west coast of Yezo, where no previous observations have 
been taken, we found water of a somewhat lesser density than is indi- 
cated for the region further off shore ; this would naturally be ex- 
pected, and agrees with the conditions found on the west coast of 
Nipon. 

Along the coasts of Sakhalin our observations agree with those of 
the Russian investigators. 

For the southern and southeastern part of the Sea of Okhotsk 
there are no previous records ; we found conditions approximately 
what would be expected and, agreeing with our observations further 
to the northward, found a local area of comparatively high salinity 
near the Kuril chain. 



26 



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